Fauna of the Permian Rocks Near Quinn River Crossing, Nevada

AN ABSTRACT OF THE THESIS OF

Dixie Jane Lernbach for the M.S. in Invertebrate Paleontology (Name) (Degree) (Major)

Date this thesis is presented August 3, 1963

Title Fauna of the Permian Rocks Near Quinn River Crossing, Nevada

Abstract approved -_.. Major Professor

The Permian rocks near Quinn River Crossing, Humboldt County,

Nevada, crop out as a north -trending block -faulted ridge and consist

of more than 2600 feet of middle Permian fossiliferous limestone.

P About 1000 feet of unfossiliferous cherty shales, sandstones, and t4 conglomerates are associated with the limestone and are assumed also

1 to be of Permian age. In addition, tertiary igneous rocks make up

part of the ridge.

Normal faults transect the ridge at several localities along

} its 9500 -foot length, and some of the beds have been folded.

The fauna of the limestone is middle and upper Leonardian in

age and consists mainly of fusulinids and associated small Foram-

inifera, solitary and colonial corals, bryozoans, and brachiopods.

The fusulinid fauna is described and illustrated as are two corals

and one bryozoan.

The fusulinid fauna is considered to be correlative, at least

-j in part, with that of the Coyote Butte Formation in central Oregon,

ad) the upper part of the McCloud Formation in northern California, the

middle Dart of the Owens Valley Formation in east central California,

and the upper part of the lower limestone member of the Garden Valley Formation and the upper part of the Carbon Ridge Formation in east central Nevada. The fusulinids are believed to be somewhat older than those of the lower Nosoni Formation in northern California and the second member of the Garden Valley Formation in east central

Nevada. FAUNA OF Ta akmIAtv ROCKS NEAR QUINN RIVER CROSSING, NEVADA

DIXIE JANE LEMBACH

A THESIS

submitted to

OREGON STATE UNIVERSITY

in partial fulfillment of the requirements for the degree of

MASTER OF SCIENCE

August 1963

L___ APPROVED:

Associate Professor of Geology

In Charge of Major

Chairman of Department of Geology

Chairman of School Graduate Committee

Dean of Craduats School .

Date thesis is presented . August 3, 1963

Typed by Ramona Nestell ACKNOWLEDGEMENTS

For the invaluable assistance they have given me during the

course of this study, I am deeply indebted to the followings

My major professor, Dr. David A. Bostwick, for suggesting this project, for his photographic assistance, and for his guidance and supervision in the field and laboratory and during the preparation

of the thesis.

Dr. W. D. Wilkinson for his constructive criticism of the thesis and for the use of his equipment.

Dr. Ira S. Allison and Dr. Jon C. Cummings for their many suggestions and their constructive criticism of the thesis.

My many friends and fellow students for their encourage- ment and understanding throughout the study and the preparation of the thesis. TABLE OF CONTENTS

Page

INTRODUCTION 1

Location 1 Geography 3 Previous Work 4 3

METHODS OF STUDY 4

STRATIGRAPHY AND STRUCTURE b i .. 5

Stratigraphy 5

Structure - 7

GEOLOGIC HISTORY - 8

FAUNAL SUMMARY . ,. 11

Age 11 Fauna 12

CORRELATIONS f 19

SYSTEMATIC PALEONTOLOGY OF THE FUSULINIDS ...... 23

Staffella sp. - 23 Schubertella aff. S. kingi 23 Schubertella sp. ; 23 Schubertella sp. 24 Pseudofusulinella cf. P. occidentalis 25 Pseudofusulinella cf. P. utahensis 27 Triticites? sp 30

Pseudofusulina cf. P. chiapasensis - 32 *'seudohsuli,na cf. P. hawkinsi 34 Pseudofusulina sp. A 35 Parafusulina cf. P. nosonensis , 36 Parafusulina sp. A 38 Parafusulina sp. B 39

BIBLIOGRAPHY .. 41

APPENDIX e Lilt

Lithologic Descriptions and Fauna 45 Tables 1.9 Plates and Explanations 64 FIGURES, PLATES, AND TABLES

Page

Figure 1. Correlation of the limestone near Quinn River

Crossing with formations . in Nevada, Oregon and California 20

Plate 1. Geologic map showing Permian rocks near Quinn River Crossing, Nevada 2

Plate 2. Columnar section of the limestone near Quinn River Crossing showing the stratigraphie distribution of the fusulinids ...... 13

Plate 3. Faunal plate 65

Plate 14. Faunal plate . . 67

Plate 5. Faunal plate 69

Plate 6. Faunal plate 71

Plate 7. Faunal plate . . . ge ... .. 73

Plate 8. Faunal plate 75

Plate 9. Faunal plate 77

Table 1. Measurements of Pseudofusulinella cf. P. __. occidentalis 149

Table 2. Measurements of Pseudofusulinella aff. _P. utahensis 50

Table 3. Measurements of Pseudofusulinella sp. A . . . r . 52

Table 4. Measurements of Triticites? sp. 53

Table 5. Measurements of Pseudofusulina cf. P. chiapasensis 55

Table 6. Measurements of Pseudofusulina cf. P. hawkinsi . . 57 ---- . . Table 7. Measurements of Pseudofusulina sp. A 59

Table 8. Measurements of Parafusulina . cf. P. nosonensis . . 60 FIGURES, PLATES, AND TABLES (CONT.)

Page

Table 9. . Measurements of Parafusullna sp. A : .' . 62

Table 10. Measurements of Parafusulina or). B . o 63 FAUNA OF THE PERMIAN ROCKS

NEAR

QUINN RIVER CROSSING, NEVADA

INTRODUCTION

One of the few reported occurrences of fossiliferous limestone

in the thick Permian sequences of sedimentary and igneous rocks in

northwestern Nevada is exposed as part of a block- faulted ridge in

central Humboldt County. The fauna of this middle Permian limestone

and the general geology of the limestone and associated unfossil-

iferous conglomerates, sandstones, shales, and igneous rocks are presented in this report. A fossiliferous limestone section 2615

feet thick was measured and sampled. The other sedimentary rocks

and the igneous rocks were mapped but their thicknesses were not measured. Because of the scarcity and poor preservation of mega -

fossils in most of the measured limestone units, the dating and

correlations were based mainly upon the fusulinid fauna.

Location

The area described is located in central Humboldt County,

Nevada, 2 miles east of Nevada State Highway 8A, 6 miles southeast of Quinn River Crossing, 36 miles southeast of Denio, and 63 miles northwest of Winnemucca, Nevada. The area covers approximately 2 square miles and extends southward from the SF4 sec. 36, T. 43 N.,

R. 32 E. and the SW sec. 31, T. 1.3 N., R. 33 E. to the NW* sec. 7,

T. 42 N., R. 33 F. in the Quinn River Crossing Quadrangle (Plate 1). 2

N r F® ..olr', 1 I

I ; y1.7,4:17.7 3 ,.u« 1

C O U N T Y

amas,,.e ru`

T 42 INDEX MAP

LEGEND

IPls Qal ti 0 Alluvium i

Tig ..m Basaltic and c". rhyolitic igneous rocks

wi+s Z ffls . Feg Qal Conglomerate, sandstone and shale

IPls

o Limestone `M Contour interval: Solid - 00 feet Dashed - 20 feet

Faults: Observed Inferred - - -

4 N

I. . . m 1 . . . , 1 I SCALE IN MILES

Plate 1. Geologic map showing Permian rocks near Quinn River Crossing, Nevada 3

Geography

The area in the vicinity of Quinn River Crossing has an arid climate, with an annual rainfall of four to five inches. The sparse desert vegetation consists chiefly of greasewood, which occurs, for the most part, on the alkali flats of the valley floors, and sage- brush, which is confined mainly to the more elevated areas.

The elevation of the valley floor just west of the outcrop of

Permian rocks is about 4100 feet, and the maximum elevation of the ridge is 4704 feet. These give a total relief of approximately 600 feet.

The ridge is cut by several small gullies, most of which have formed along east -trending faults. Drainage is mainly to the west.

Previous Work

Muller has reported the presence of Wolfcampian and lower

Leonardian fusulinids in the limestone near Quinn River Crossing, and he considers the outcrop to represent an eastward extension of the McCloud Formation of California (9, p. 1781). However, he does not name the forms upon which he based this correlation or further elaborate upon the outcrop. No other reference to the outcrop seems to have been made in previous published reports or surveys.

The nearest reported outcropping Permian strata occur in the

Black Rock area about 30 miles southwest of Quinn River Crossing.

According to Gianella, the Black Rock Permian consists of over

1800 feet of volcanic sediments and limestone, some of which contains upper? Permian brachiopods (14). The brachiopods have not 4 been described, and so the faunal and age relationships of these

Permian sediments to those near Quinn River Crossing are not known at this time.

METHODS OF STUDY

One week in each of the months of March, July, and September

1961 was spent in the field measuring the section, collecting samples, and mapping the outcropping beds. The field mapping was done on air photos with a scale of 1/20,000 and transferred later to an enlarged portion of the advance print of the Quinn River Crossing Quadrangle.

The limestone beds were sampled at stratigraphic intervals not more than 50 feet apart. The samples were slabbed, chips containing properly oriented specimens were cut from the slabs, and thin sections of fusulinids and other fossils were made from the chips. The peel method, described by Buehler (4), was tried on a few representative samples, but the preservation of the fossils was such that more detail could be obtained from thin sections.

Measurements of the fusulinids were made from oriented axial and sagital sections, and tabulated measurements for most of the species are included in the appendix.

Silicified megafossils were obtained from some of the lime- `/ stone samples by etching them in three to four normal HC1. A few microfossils were obtained in this manner, but for the most part they were too poorly preserved to be identified. 5

STRATIGRAPHY AND STRUCTURE

The area under consideration is a north - trending block -faulted

ridge of typical Basin-and -Range type with a west -facing fault scarp.

It is about 9500 feet long and consists of limestone, shale, sand-

stone, conglomerate, and igneous rocks. The ridge is cut by several

east -trending faults, some of which cause offsets within the lime-

stone section.

Stratigraphy

The north end of the ridge is composed of approximately 1000

feet of medium bedded (12 to 4 feet) to thick bedded (over 4 feet)

varicolored cherty shales, sandstones, and conglomerates (Plate 1).

These - clastic sedimentary rocks are tentatively referred to the

Permian System; however, they are unfossiliferous and are not

visibly in contact with the middle Permian limestone. Thus, the

age relationship of these rocks within the Permian cannot be

determined at this time.

The shales have thin, colored laminations and a coarse blocky

fracture. They range in color from black to tan. The black shales

contain euhedral pyrite crystals, some of which are as much as one-

half millimeter in diameter.

The coarser elastics range from fine sandstones to pebble conglomerates and consist of subangular to subrounded chert, metaquartzite, and slate particles in a fine- grained chert matrix.

The sandstones appear to be well sorted but the conglomerates are very poorly sorted. Graded bedding was observed in these rocks on 6 some freshly fractured surfaces. The presence of silt- to sand- sized carbonate inclusions in the chert matrix suggests that these elastics were deposited in an alkaline environment. Although a few small quartz overgrowths were observed, most of the boundaries between the clastic particles and the matrix are sharp; therefore, the chert matrix is assumed to be syngenetic. This fits well with

Bissell's conclusion that at least 95 percent of the silica cement in

Upper Paleozoic sediments of the Cordilleran area is syngenetic

(2, p. 185).

The chert conglomerates are lithologically similar to a bed of chert conglomerate (unit 11) in the limestone section. This similarity suggests that these rocks had the same provenance.

The middle Hart of the ridge consists of 2615 feet of fossiliferous limestone (Plate 1). This limestone is thin -bedded to massive, microcrystalline to coarse -crystalline, dark gray to black on fresh surfaces, and contains numerous cherty beds, chert stringers and irregular chert masses. Bedded cherts (unit 16) also are present.

Detailed lithologic descriptions of the units comprising the limestone section are presented in the appendix.

A small exposure of limestone just to the east of the main ridge may be an eroded part of the main ridge or, more probably, an erosional remnant of another fault block of the same limestone. Two random samples were taken from this exposure, and they were found to be lithologically and faunally similar to, and in the same stratigraphic order as, units 7 and 12 of the measured section. 7

A zone of igneous rocks, which consists of rhyolite, basalt and

basaltic breccia and porphyries, is present between the cherty clastic

sedimentary rocks and the limestone (Plate 1). Some of these igneous

rocks seem to be of an intrusive nature, but exposures are poor and no

contact between them and the antecedent country rock was observed.

These rocks may represent feeder dikes and basalt and rhyolite flows,

remnants of which also occur in a second igneous zone at the south

end of the ridge (Plate 1) and on the ridges surrounding the area.

Altered tuffs also are present in the igneous zone to the south. The

rocks in both of these igneous zones are similar to the middle

Tertiary rhyolites and basalts reported in northeastern and north-

western Nevada by Roberts (25) and other authors; therefore, the igneous

rocks are assumed to be Tertiary in age.

The valley floor west of the ridge consists of late Tertiary and

Quaternary lake beds overlain by Quaternary alluvium.

Structure

Several east -trending faults cut across the block- faulted ridge

near Quinn River Crossing (Plate 1). One of these occurs between

the cherty clastic sedimentary rocks at the north end of the ridge

and the northern zone of igneous rocks. Another fault is believed to

separate the igneous zone from the limestone section; the limestone,

in turn, is separated by a fault from the zone of igneous rocks that

comprise the south end of the ridge. The attitudes of these faults and the stratigraphie separation could not be determined. E;

The average strike and dip of the limestone beds is N. 22° E.,

63° SE. The average trend of the cherty clastic rocks is N. 45° E.,

60° SE., and that of the layered igneous rocks is N. 30° E., 45° SE.

A few of the basalts in the northern igneous zone dip about 45° NW. and the rhyolites and basaltic porphyries in this same zone trend

N. 80° W. and have an apparent dip of 45° NE.

Several easily recognizable fossiliferous beds served as horizon markers and permitted recognition of four east -trending, faults within the limestone section. Three of these faults cause offsets which range from approximately 200 to 500 feet, but the fault which occurs between the lower 2100 -foot part and the upper 535 -foot part of the section may have produced an offset of greater extent and will be discussed later. The attitudes of these faults could not be determined. Tan- to buff -weathered rhyolite dikes occur along the fault in the thin -bedded siliceous limestone at the south end of the section.

Minor folds and faults occur in the outcrop of cherty shales, sandstones, and conglomerates, and a small anticlinal fold is exposed at the southern end of the limestone outcrop.

GEOLOGIC HISTORY

The lithology and fauna of the rocks near Quinn River Crossing indicate that this area is near the eastern boundary of the eugeosynclinal facies of the Cordilleran geosyncline, which covered the present area of the Great Basin from late Pre- cambrian to early

Tertiary time. 9

According to Osmond (24), the geosyncline was divided during the early Paleozoic by a north -northeast trending tectonic zone through

central Nevada the Antler orogenic belt of Roberts - (2q, forming an eastern miogeosynclinal zone of shallow -eater carbonates and a western eugeosynclinal zone of deeper-water elastics, volcanics, and subor- dinate carbonates. The tectonic zone rose and expanded to the east and west until, by early Tertiary time, it included the former area of the geosyncline (2I). Osmond states further that this rise and expansion was accompanied by deformation which was especially intense in t'ississippian (Antler), Jurassic- Cretaceous (fevadan), and Cretaceous -

Tertiary (Laramide) times (24).

During the late Paleozoic, according to Sharp, deposition in northwestern Nevada took place in several deep basins rather than in a single large enicontinental sea (27). The sedimentary rocks near

Quinn River Crossing were deposited during middle Permian time in a warm, relatively shallow near -shore environment in one of these basins. The coarse cherty clastic rocks and the fauna of the limestone have closer affinities to eugeosynclinal deposits and faunas in central Oregon and northern California than to miogeosynclinal deposits and faunas to the east. Some fluctuation in sediment supply or water level is indicated by the presence of the chert conglomerate (unit 11) within the limestone section. The major late Paleozoic rock types that have been described from northwestern

Nevada are similar to those near Quinn River Crossing and include quartzite, slate, chert, volcanics and minor amounts of limestone. lo

These rock types have lithologic affinities with those found in

northern California and central Oregon, according to Ferguson (13).

Bissell states that much of the Upper Paleozoic volcanism was in the

form of submarine flows (2, p. 179). According to Douglas, extensive

thrusting, primarily in the Mesozoic, resulted in the juxtaposition

of contemporaneous deposits of the eastern and western Paleozoic

facies in several localities in northern and central Nevada (8).

Dunbar suggests that the Laramide thrusting may have continued

into the Eocene and that the scarcity of Eocene and Oligocene strata

is due to the high mountainous surface and exterior drainage of the

Basin and Range region during early Cenozoic time (10, p. 417).

King, however, states that during this time the western area of the

Great Basin was a 'flow- upland' which had a worn down and deeply

decayed surface (16, p. 156). According to Lovejoy, much of this

area was covered later by Mio- Pliocene Lake Nevada and by its

Pleistocene successor, Lake Lahonton (18).

Basaltic and silicic volcanic flows were numerous and wide-

spread in the Quinn River area during Miocene and Pliocene times,

and the volcanism was accompanied by block faulting and folding

(35, p. 26).

According to Osmond, the faulting decreased in frequency in the

late Tertiary with the cessation of volcanism, but movement along the

faults has continued since the Miocene (2L).

The post Mio- Pliocene elevation of the Cascade, Klamath and Sierra

Nevada (1) mountain ranges resulted in lowered rainfall over the . western Nevada lowlands to the east, and the lake waters gradually 11 receded. Subaerial erosion followed and has continued to the present.

FAUNAL SUMMARY

The fauna collected from the measured limestone section near

Quinn River Crossing is considered to be middle and upper Leonardian

(Permian) in age and consists of fusulinids and associated small

Foraminifera, corals, bryozoans, brachiopods, and minor fossil constituents. The only significant difference between this and most other described Permian faunas of the western United States is the apparent absence of cephalopods. It is assumed that if any are present in the outcrop they are rare.

All of the fossils collected were embedded in dense limestone, and the calcareous specimens could be studied only in slabs or in thin sections. The partly silicified fossils obtained from the uppermost unit of the section were etched from their matrix and identifications were made from the freed specimens.

AgE

The middle and upper Leonardian age of the fauna is based upon the ages previously assigned to faunas of other formations which contain species or faunal associations similar to those obtained from the beds near Quinn River Crossing. The lower 2100-foot part of the section is assigned a middle Leonardian age because it contains several fusulinid species which most closely resemble forms generally reported to range below the middle Leonardian and one fusulinid species which is closely similar to, but seemingly somewhat more primitive than, 12

forms generally reported to be lower Wordian in age. The upper

535 -foot part of the section contains only the last species and is

considered to be upper Leonardian or perhaps younger. A columnar

section of the limestone showing the stratigraphie distribution of

the fusulinids is shown in Plate 2.

Fauna

Specimens of Climacammina, Geintzina, Cribrostomum, and Textularia

were identified from slabbed material obtained from several units

throughout the section. The etched residue from unit 20 contained

several very poorly preserved foraminiferal specimens. Of these,

however, only a specimen of Textularia could be identified.

A few of the fusulinid generic groups have restricted strati-

graphic ranges over wide areas and thus are useful as "zone fossils"

for interregional correlations. The genus Parafusulina is one of

these "zone fossils" and its presence has been used by other authors

to designate the Leonardian to lower Guadalupian (Wordian) "Zone of

Parafusulina" (32, p. 21f). Intense septal fluting and the presence of

cuniculi were the original criteria used to distinguish Parafusulina

from similar genera; however, according to Thompson, "cuniculi have

since been observed in Permian fusulinids obviously not generically

related to [the genotype] Parafusulina wordensis" (32, p. 55).

Of those fusulinids collected from the limestone near Quinn River

Crossing, cuniculi were observed in all properly oriented specimens which have a two -layered, or Triticites, wall. These include two species which are more or less typical of the genus Parafusulina. 13

Parefu.ulln. cf. P. nosonensls

Parefusullne cf. P. nosonensls

Unit 020

taffella sp. }farefusullna cf. P. roscncnsls Unit 119 Schubertelle sp.

Unit - 018 OM M me Unit #17 I Schubertella sp.? f e Fault uuuueniieaie..+Fd9 Unit 016 Ei:Rr.t3

11 1 ENE Se 111 i. s>_ 1 I , I 1 C;

Unit 015

Schubertella sp.

Parafusulina sp. B PseudofuNli-11. cf. P. occidental]. Unit 014 chubertell. sp.

Unit 013 Steffens sp. Schubertella sp. Unit 912 Pssudofusul1ne11a cf. P. occidental!' Unit 011 Q - Paratusulina cf. P. nosonensls 1 1 }subertehbo ep. ssudofusulina cf. P. hawking! seudofusulinolla off. P. utehensls

3ohubertells sp. Par.tusulina sp. B Unit 010

Parafu.ullna cf. P. nosonensis Paratusullna sp. B ssudofusulinslla aft. P. utahenale bertells sp. nlay! I

I 1 L I -- Unit 09 _ -_-m_ee--- Staffells sp. l Unit" MIM-e-Me-raramwem Parofusullna so. B ma----- I Triticites? sp. NNNc IMO ...... 1u------N- Triticlte.T sp. -u------narMea= s------N..L ------Parefusullna cf. P. nosonensis Unit 07 u------MNNNNMMO - P.sudofusullne cf. P. chlepesensls }p.eudofusullnella off. P. utahenels u------Schubertell p, Pseudofusulinella aff. P. utahensi. }Pssudofu.ullna cf. P. chlapoeensle ------u.as- Sehutertella p, mamma= am Pseudofusullna cf. P. chlaossensls ' --- Schubertellx FF - aff. P. utahensls Fault w..uiuiuurniuiiux -- iauiu_ BOCK --- LEGEND ------7Yit1clLiitaspff.IohuWltel¡a aff. S. kingi Pseudotusulínella cf. P. occidental!. ------I ----- Puou.uina cf. hwklnsl ------1. Unit 06 as---s-- sp. ® Pssudofusulíns sp. A Limestone ----- IB SCALE MET ------I Pseudofusulinella cf. P. occidental!. ------es----- [100 t1ak.''-_ ------Conglomerate Unit 05 I ....immommmmmemmemm Unit 03 Pseudcfueulinella sp. A 0 =, Parafusullns s0. A Unit 01 Chart

. Plate 2. Columnar section of the limestone near Quinn liver Crossing showing the stratigraphie distribution of the fusulinids. ]1:

Forms referred to Parafusulina sp. A occur in unit 1 of the section

and forms referred to Parafusulina cf. P. nosonensis occur in a few units near the middle and in the uppermost unit (unit 20) of the

section. Therefore, the entire limestone section is considered to be within the "Zone of Parafusulina." Of the other species which possess

cuniculi, one is referred to Triticites ?, three to Pseudofusulina, and one to Parafusulina. Until now, no described form possessing cuniculi has been assigned to the genus Triticites. The reasons for doing so

in this paper are presented in the description of Triticites? sp. in the Systematic Paleontology section.

The lower 2100-foot part of the limestone section contains the following species of fusulinids:

Staffella sp.

Schubertella aff. S. kings (Dunbar & Skinner)

Schubertella sp.

Pseudofusulinella cf. P. occidentalis (Thompson & Wheeler)

Pseudofusulinella aff. P. utahensis (Thompson & Bissell)

Pseudofusulinella sp. A

Triticites? sp.

Pseudofusulina cf. P. chiapasensis (Thompson & Miller)

Pseudofusulina cf. P. hawkinsi (Dunbar & Skinner)

Pseudofusulina sp. A

Parafusulina cf. P. nosonensis (Thompson & Wheeler)

Parafusulina sp. A

Parafusulina sp. P 15

Most of these species resemble forms which have been reported from beds of Leonardian age. Thompson and Wheeler described Pseudofusulinella occidentalis from the lower Leonardian upper McCloud Formation in northern California (34, p. 25 -26). A form resembling Pseudofusulinella occidentalis also occurs with forms which are similar to Pseudofusulina chiapasensis and Pseudofusulina hawkinsi in the Leonardian Coyote Butte

Formation near Suplee in central Oregon. Triticites? sp. is very similar to a form which Chen has described as Triticites truncatus from the Lower Artinskian (Lower Leonardian) Swine Limestone in South China

(5, p. 39). Pseudofusulina chiapasensis was described by Thompson and

Miller from the Grupera Formation in Southern Mexico (33, p. 484).

Pseudofusulina hawkinsi was described by Dunbar and Skinner from the middle Hueco and lower Leonard formations in west Texas (11, p. 633), and it also has been reported with specimens of Parafusulina from the lower Moorman Ranch member of the ?'eouop Formation in Eureka County,

Nevada (29, p. 106). An association of specimens of Pseudofusulina and

Parafusulina was reported by Henbest from the upper part of the Carbon

Ridge Formation in the Diamond Mountains east of Eureka, Nevada (23, p. 66). Specimens of Pseudofusulina and Parafusulina also occur together in the middle part of the Owens Valley Formation in the South

Ingo Mountains of California (22, p. 11). The upper part of the lower limestone member of the Garden Valley Formation contains specimens identified as " Triticites" sp. and Parafusulina sp. which, according to

Henbest, is intermediate between Schwagerina linearis Dunbar and Skinner and Parafusulina lineata Dunbar and Skinner and which has more axial

filling than P. nosonensis Thompson and Wheeler (23, p. 68). 16

The upper 535 foot part of the section is separated by a fault

from the lower part of the section. These upper beds contain Para -

fusulina cf. P. nosonensis in association with a few specimens of

Staffella sp. and Schubertella sp. The more primitive fusulinids

found in the lower part of the section are absent in the upper part.

The fault between the two parts of the section makes it virtually

impossible to determine their exact stratigraphic relationship, and,

although there appears to be no repetition of beds or faunas across

the fault, it is possible that some intervening beds have been faulted

out of the section. Specimens of Parafusulina nosonensis were ké described by Thompson and rheeler from the lower Nosoni Formation

(34, p. 33 -34). Similar specimens were reported by Henbest from the

upper part of the lower limestone member of the Garden Valley formation

(23, p. 58) and by Steele from the second member of the same formation

(29, p. 103).

Two beds containing abundant colonial corals are present in the

section. One occurs near the middle of unit 7 and the other near the

middle of unit 15. These corals are loosely aggregated and have been

assigned to the genus Waagonophyllum (Plate 9). They resemble specimens of Waagonophyllum washburni Merriam and Waagonophyllum ochocoensis

Merriam which have been described from the Coyote Butte Formation

(20, p. 375 -376). Large, poorly preserved solitary corals occur in the lower part of the section and seem to be most closely related to cyathophylloid corals described by Merriam from the Coyote Butte

Formation (20, p. 380). Compact colonial corals comprise nearly the whole of the exposed portion of unit 3. Some of the corallites are 17 very similar to specimens which Merriam has identified as Litho- strotion? genomorph Diphystrotion sp. from the Coyote Butte Formation

(20, p. 380). However, individuals which appear to belong to the genomorph Diphyphyllum, as defined by McLaren and Sutherland (19, p.

626), also are present. The latter forms in unit 3 are similar to specimens described by Easton from Nevada and California (12, p. 579).

The genomorph concept in corals is important to coral taxonomy and is restated here. The term " genomorph" was first used by Smith and / Lang to express a trend "which some external or internal stimulus has provoked to rapid development in a colony or in certain individuals of a colony" (28, p. 179). It does not constitute a true genus, but "is the forerunner of an evolution which may take place in closely or distantly related stocks and may give rise to new generic forms"

(28, p. 179). Hill has listed the possible developmental trends of the genus Lithostrotion and concluded that all of these trends might be found in the same individual (15, p. 83). According to McLaren and

Sutherland, however, it is more common for only one trend to be pro- nounced, and such individuals may be united in "genomorphic groups"

(19, p. 627). The genomorphs Diphyphyllum and Diphystrotion, then, are the trends exhibited by the corallites which form the Lithostrotion colony comprising unit 3 (Plate 8, fig. 5-7).

Specimens of Bryozoa referred to the genus Rhombotrypella (Plate 8, fig. 1 -4) occur in units 1 and 12, and they are especially abundant in beds near the top of unit 20. This genus has been reported by Duncan from the upper (Leonardian) part of the Carbon Ridge Formation near

Eureka, Nevada (23, p. 66) and has been identified from the Coyote le

Butte Formation in central Oregon. Species belonging to this genus have been described by Nikiforova from the Permian of Russia (3, o.279), but, as yet, none seems to have been described from North America.

Partly silicified brachiopods vere obtained from several beds in unit 20. These were identified as follows:

Steinoscisma sp.

Crurithyris sp.

Composita spp.

Schuchertella sp.

Derbyia sp.

Chonetes sp.

Spiriferella sp.

Spiriferina cf. S. billingsi Schumard

Punctospirifera aff. P. campestris (White)

Dialasma sp.

Productid fragments

Some of the above identifications were made from incomplete specimens, and only two specimens were preserved well enough to be referred with reservation to particular species. Similar middle Permian brachiopod faunas have been reported by Stehli from the Bone Spring limestone in

West Texas (30, p. 263 -358), by Cooper from the Coyote Butte Formation in central Oregon (6, p. 1 -79) and from Sonora, Mexico (7, p. 22 -76), and by Nolan et al, from the Carbon Ridge Formation near Eureka, Nevada

(23, p. 66).

The gastropod Baylea sp. is associated with the brachiopods in unit 20. It also has been found in some of the formations mentioned 19 above, but its range is too long for it to be of value as an age

indicator. Two other gastropods were found but were not preserved

i well enough to be identified.

Tubular structures tentatively identified as worm tubes are relatively common in several beds throughout the section.

Round crinoid columnals are present throughout the section and are very abundant in some beds; however no other crinoid parts were observed.

Two poorly preserved ostracod valves were obtained from the etched residue from unit 20. These were not identifiable.

CORRELATIONS

On the basis of faunal similarities, the limestone section near

Quinn River Crossing is considered to be approximately equivalent in age to the Coyote Butte Formation in central Oregon, the upper part of the McCloud Formation in northern California, the middle part of the Owens Valley Formation in east central California, and the upper part of the lower limestone member of the Garden Valley Formation and the upper part of the Carbon Ridge Formation in east central Nevada

(Fig. 1).

The age of the fauna of the Coyote Butte Formation was first discussed by Merriam and Berthiaume. They reported that the fusulinids, corals, and brachiopods indicated a Permian age but the fusulinids implied that the formation is not lowest Permian. They further stated that Cooper believed the brachiopods indicated a lower Permian Age (21, p. 157 -158). Cooper later assigned a Vordian A m e r i c a n Northwest North Central Nevada Central C a l i f o r n i a S t a n d a r d Nevada Klamath Inyo S e c t i o n Humboldt Oregon E u r e k a A r e a Mountains Range County (9) (29) S91 (9) (9) _ _

Garden 1 5' Valley Nosoni Guad. Formation ti 3o Second Formation Member p-

------?-- s Limestone _ J_ Owens near Coyote Quinn 1 Butte = Leonardian River _f -9 L' Valley Garden Crossing 4, ' Formation r ,? y m Valley -' - T McCloud Formation Carbon Formation.

1 w Lower Ridge Formation Member Formation

Riepetown Riepetown Wolfcampian Sandstone Sandstone

Fig. 1. Correlation of the limestone near Quinn River Crossing with formations No in Nevada, Oregon and California. Numbers at heads of columns refer to references in the bibliography. 21

age to the formation because of the presence of the brachiopod

`uirwoodia (6, p. 18). Henbest, however, observed that the fusulinids

resemble Upper Wolfcampian and Leonardian species rather than those

found in the Word formation or its equivalents (9, p. 1781). The

fusulinid fauna of the limestone near Quinn River Crossing more closely

resembles that of the Coyote Butte Formation than that of any other

formation described up to this time.

The upper part of the McCloud Formation was assigned a Leonardian

age by Thompson and Wheeler on the basis of the fusulinid fauna

(34, p. 11) .

Williams determined that the age of the brachiopod fauna of the

middle part of the Owens Valley Formation is probably Leonardian or

younger (22, p. 12), and Merriam and Hall concluded that it is the

same age as the Carbon Ridge Formation on the basis of the fusulinid

and cephalopod faunas (22, p. 12).

Henbest has studied the fusulinid fauna from the upper part of

the lower limestone member of the Garden Valley Formation. He con-

cluded that a late Hueco (Wolfcampian) or more likely Leonard age is

indicated (23, p. 68). Steele, however, states that the basal lime-

stone member contains middle Wolfcampian fusulinids and that it

. correlates faunally with the middle Wolfcamnian Riepe Spring limestone

(29, p. 112). As he does not mention the characteristically Leonardian

genus Parafusulina, which was previously identified by Henbest from the

. upper part of the member, it is assumed that Steele did not study the

entire fauna and, therefore, wrongly assigned a middle Wolfcampian age

to the entire member. 22

According to lienbest, the fusulinid fauna of the upper part of the Carbon Ridge Formation probably is not older than upper Hueco, and may be Leonardian or even as young as the lower part of the Nosoni

Formation (23, p. 66).

Two other formations in east central Nevada are believed to extend

into the Leonard and may be partly equivalent to the limestone near

Quinn River Crossing. Henbest has determined the fusulinid fauna from the lower beds of the Havallah Formation in the 'Plinnem.cca Quadrangle to be of Tolfcampian and possibly Leonardian age but, according to

Roberts, no fossils have been found in the upper beds of this formation

(25). Fusulinids of possible Leonard age also have been reported by

Langerhebuì et al. from the Arcturus Formation in the Shell Creek Range in Lincoln County, Nevada (17, p. l54).

Fusulinids in the limestone section near Quinn River Crossing

referred to Parafusulina cf. P. nosonensis resemble but perhaps are not conspecific with the type specimens of the species described from the

lower beds of the Nosoni Formation. Representatives of Parafusulina nosonensis in the lower Nosoni, as well as forms identified as Para- fusulina cf. P. nosonensis from the second member of the Garden Valley

Formation, occur in association with morphologically more advanced forms of Parafusulina. No such association was observed in the limestone section near Quinn River Crossing. For this reason, the beds containing Parafusulina cf. P. nosonensis in the limestone section are believed to be older than, and therefore not correlative with, those of the lower Nosoni Formation and the second member of the Garden

Valley Formation. 23

SYSTEMATIC PALEONTOLOGY OF THE FUSULINIDS

STAFFELLA SP,

Poorly preserved specimens referable to the genus Staffella were observed in several samples collected throughout the section. Because of their small size and the fact that most of them are mineralized, they were not measured or illustrated.

Remarks. Staffella is widespread in North America in rocks of

Middle Pennsylvanian to Late Permian age.

Occurrence. Forms of Staffella sp. are present in units 8, 12, and 20.

SCHUBERTELLA aff. S. KINGI

Dunbar & Skinner, 1937

Plate 3, figure 1

Schubertella kingi DUNBAR & SKINNER, 1937, Univ. Texas, Pull. 3701,

p. 610-611, pl. 45.

Only a few improperly oriented and poorly preserved specimens of

Schubertella aff. S. kingi were found in the section. Tests of these specimens are minute, elongate fusiform, and have bluntly rounded poles. They have an endothyroid juvenarium of at least one volution that has an axis of coiling approximately at right angles to that of the succeeding volutions. Specimens appear to have five volutions, of which at least the outer three are fusiform: 24

The proloculus is minute, the tunnel is essentially straight,

and the tunnel angle increases from about 26° in the first fusiform

volution to 38° in the last volution. Chomata are small, narrow,

and rounded, and more prominent in the outer volutions.

The extremely thin spirotheca consists of a tectum and lower

light layer and is practically invisible over the tunnel. No septal

fluting was observed.

Measurements other than the tunnel angles were not made because

of the lack of properly oriented specimens.

Remarks. This form closely resembles specimens of Schubertella

kingi Dunbar and Skinner, which was first described from the Hueco

Formation in West Texas (11, p. 611). Its affinities to this form,

however, could not be determined because of the lack of oriented

specimens. Forms of Schubertella kingi also have been reported from

middle Wolfcampian rocks in Texas, Kansas, Nebraska (11, p. 611),

Utah, and California (34, p. 25). Schubertella aff. S. kingi differs

from specimens of S. melonica Dunbar and Skinner and S. mullerriedi

Thompson and Miller in its smaller size and less inflation.

Occurrence. Schubertella aff. S. kingi is present in unit 6.

SCHUBERTFLLA SP.

Poorly preserved specimens referable to the genus Schubertella were observed in collections from several units throughout the section, but no properly oriented specimens were obtained. Specimens of this species were not measured or illustrated. 25

Remarks. These specimens may be the same as Schubertella aff.

S. kingi, which was found lower in the section, . but insufficient

material, . along with the poor condition of the specimens, made com- parisons uncertain. Schubertella is very widespread in North America and ranges from Upper Pennsylvanian to Late Permian.

Occurrence. Schubertella sp. is present in units 7, 10, 12,

14, 15, 17 ?, and 20.

PSEUDOFUSULINt LLA cf. P. OCCIDENTAL'S

(Thompson &heeler, 1916)

Plate 3, figures 5-7

Neofusulinella occidentalis THOMPSON & WHEELER, 1946, Geol. Soc.

Amer. Mem. 17, pt. 1, p. 25-26, pl. 2, fig. 1-4.

Pseudofusulinella occidentalis (THOMPSON & WHEELER). Thompson,

1951, Cushman Found. Foram. Research, Contr., Vol. 2, p. 118,

pl. 12, fig. 6 -11.

Tests of Pseudofusulinella aff. P. occidentalis from the limestone near Quinn River Crossing are small, inflated fusiform, and have bluntly pointed poles and a straight axis of coiling. Three specimens of nine volutions are from 3.0 to 4.0 mm long and from 1.9 to 2.4 mm wide. The average length and diameter are 3.5 mm and 2.2 mm respectively. The form ratio stays about the same throughout, although in some specimens there is a slight increase with growth to about the fourth volution and a slight decrease in the outer volutions.

The average form ratio for the ninth volution of 3 specimens is 1.6 and 26

the maximum for this volution is 1.7. The maximum form ratio occurs

in the fourth volution and is 2.3.

The proloculus is small and has an average outside diameter in

3 specimens of 115 microns. The shell shows uniform expansion to the

fourth or fifth volution, after which the chambers of most specimens

tend to become slightly more inflated.

The tunnel is singular, high and narrow, and fairly straight.

The chomata are well-developed and asymmetrical, and they commonly

reach the tons of the chambers.

The spirotheca is thin and consists of an upper tectorium, tectum,

and diaphanotheca. Extensions of the massive chomata in some specimens

give the wall a four-layered appearance over the tunnel. The wall

thickness increases gradually from an average of 24 microns in the

second volution of 4 specimens to a maximum of 107 microns in the ninth

volution of 1 specimen. The septa are thin, numerous and broadly

fluted. The fluting increases in intensity toward the poles. Measure-

ments of specimens referred to this species are given in Table 1.

Remarks. This form resembles specimens of Pseudofusulinella

occidentalis (Thompson and Wheeler), which was originally described

from the basal McCloud Formation in northern California (34, p. 25 -26),

but it differs from the McCloud forms in its smaller size, smaller form

ratio and greater wall thickness. It can be distinguished from speci-

mens of Pseudofusulinella montis (Thompson and feeler) by its smaller

size and more highly inflated chambers. Forms nearly identical to

Pseudofusulinella cf. P. occidentalis occur in the central Oregon

Coyote Butte Formation of middle Leonardian age. 27

Occurrence. Pseudofusulinella cf. P. occidentalis is present in units 6, 12 and 15.

PSEUDOFtSULINFLLA aff. P. UTAHENSIS

Thompson & Bissell, 1954

Plate 3, figures 2 -4

Pseudofusulinella utahensis THOMPSON AND BISSELL, 1954, Univ. Kans.

Paleont. Contr., Protozoa, Art. 5, P. 34 -35, pl. 7, figs. 1 -10.

Tests of Pseudofusulinella aff. P. utahensis are small, elongate fusiform, and have sharply pointed poles, highly inflated central regions, concave lateral slopes, and irregular axles of coiling. Two specimens of 7 volutions average 3.9 mm in length and 2.7 mm in width.

The form ratio increases gradually from a minimum of 1.0 in the first volution of 1 specimen to a maximum of 2.0 in the fourth volution of another. The average form ratio for the seventh volution of 2 specimens is 1.5. There is a uniform polar elongation with growth.

The proloculus is small and spherical. The outside diameter in

8 specimens ranges from 110 to 140 microns and averages 128 microns.

The chambers are of about equal height throughout the length of the shell.

The tunnel is singular, high and narrow, and slightly irregular.

The chomata are massive and asymmetrical, with steep to overhanging tunnel margins and moderate to steep polar sides. The chomata commonly extend to the tope of the chambers in the outer volutions. 28

The spirotheca is thin and composed of an upper tectorium, tectum, and diaphanotheca. The wall thickness increases rather uniformly from about 25 microns in the first volution of 7 specimens to 70 microns in the seventh volution of 1 specimen. The septa are thin and numerous, moderately fluted in the axial and polar regions, and relatively unfluted across the central part of the shell. Measurements of specimens referred to this species are given in Table 2. ___Remarks. This form most closely resembles specimens of Pseudo - fusulinella utahensis Thompson and Bissell which was originally described from specimens obtained 1000 feet above the Pennsylvanian-

Permian contact in the Oquirrh Formation in the southern Wasatch '

Mountains near Provo, Utah (31, P. 3h -35), and which also has been reported from beds of Lower Permian age in other parts of western

North America. The form described here differs from the type specimens in having smaller form ratios, a straighter and more narrow tunnel, and more uniform expansion. It does not closely resemble any other described form of Pseudofusulinella.

Occurrence. Pseudofusulinella aff. P. utahensis is present in units 7 and 10.

PSEUDOFUSULINELLA SP. A

Plate 3, figures 8 -9

All of the specimens of Pseudofusulinella sp. A appear to have been distorted by compression during or after preservation; therefore, measurements other than those of the wall thickness and proloculus 29 diameter were not considered to be reliable and are not given here.

Tests of this form are small and inflated fusiform. They have sharply pointed poles and slightly concave lateral slopes. Most specimens appear to have from five to six volutions; however, the preservation of the outer volutions is very poor, and there are some indications that some of these forms may have had one or more additional volutions. There appears to be an irregular polar elongation with growth, but most of this may be due to compression.

The proloculus is small and spherical, and its outside diameter in 14 specimens ranges from 112 to 218 microns and averages about 150 microns. The chambers show little inflation and tend to exhibit a slight increase in height toward the poles.

The tunnel is singular and fairly straight. Chomata are asymmetrical and moderately well developed. They extend to the tops of the chambers in a few specimens, but in others they are low.

The spirotheca is thin and composed of an upper tectorium, tectum, and diaphanotheca. The wall increases uniformly in thickness and averages 30 microns in the first volution of 6 specimens and 90 microns in the fifth and sixth volutions of 4 specimens. Septa are thin, fairly numerous, and moderately fluted in the polar regions. Measure- ments of specimens referred to this species are given in Table 3.

Remarks. This form resembles specimens of Pseudofusulinella aff.

P. utahensis, which is found higher in the section, but it differs in being less inflated and in having lower and less massive chomata.

Occurrence. Pseudofusulinella sp. A is present in unit 1. 30

TRITICITES? SP.

Plate 3, figures 10 -16) Plate 4, figures 1-5

Tests of Triticites? sp. are of moderate size, elongate cylindrical, and have very bluntly rounded, or truncated, poles. Two specimens of 7 volutions are about 1.6 mm in width and 2.9 mm in length. The first volution appears to be coiled nearly at right angles to the other volutions, and the tests appear to have a somewhat irregular axis of coiling throughout the later volutions. The form ratio increases with growth from a minimum of 1.0 in the second volution to an average of

1.8 in the seventh volution. The maximum form ratio observed is 2.2 in the sixth volution.

The proloculus is small and spherical. The outside diameter in

11 specimens ranges from 56 to 120 microns and the average is 85 microns. Expansion of the shell is irregular, and there is some variation in the axial profile.

The spirotheca consists of a tectum and moderately coarse keriotheca. The wall thickness increases with growth from 10 to 17 microns in the first volution to a maximum of 74 microns in the sixth volution of 1 specimen. Septa are thick and fairly numerous, strongly and highly fluted in the axial region, but almost straight across the central part of the shell. Well- developed cuniculi are present.

The tunnel is singular, low, broad, and fairly straight. The chomata are small and asymmetrical; they are well developed only in the inner volutions and were not observed past the fifth volution.

Measurements of specimens referred to this species are given in Table 4. 31

Remarks. Triticites? sp. closely resembles in most respects specimens of Triticites truncatus Chen which were described from the

Lower Artinskian (Lower Leonardian) Swine limestone in South China

possess- (5, P. 39). It differs significantly from the Chinese form in ing cuniculi. No forms previously referred to Triticites by other authors have been characterized by possession of cuniculi. However, specimens of Triticites? sp. more closely resemble described species of Triticites than they resemble forms referred to any other genus.

Moreover, specimens of Triticites? sp. do not, except for possession of cuniculi, bear a close resemblance to any species of genera charac-

terized by cuniculi. In view of the general resemblance . to well known forms of Triticites, it seems best to refer the specimens found in the limestone near Quinn River Crossing to Triticites, with question. It is fully recognized that these forms may, upon further study, prove

c more closely related to Parafusulina or some other genus known to possess cuniculi. Inasmuch as the forms in the Swine limestone and in the limestone near Quinn River Crossing occur in rocks which are considered to be of an age at or beyond the generally accepted upper age limit of Triticites and inasmuch as cuniculi have been observed in the more advanced forms of several genera other than those characterized by the presence of cuniculi, it is concluded that the development of cuniculi may very possibly have taken place within advanced and aberrant forms of the genus Triticites.

Occurrence. Triticites? sp. is present in units 6 and 7.

J 32

PSEUDOFUSULINA cf. P. CHIAPASENSIS

(Thompson & Miller, 1944)

Plate 4, figures 6 -7; Plate 5, figures 1 -8

r Schwagerina chiapasensis THOMPSON & MILLER, 1944, Jour. Paleon.,

Vol. 18, No. 6, p. 4944 05, pl. 83, fig. 1, 2; pl. 84, fig.

1-3.

Pseudofusulina chiapasensis (THOMPSON & MILLER). Thompson, 1948,

Univ. Kans. Paleont. Contr., Protozoa, Art. 1, p. 52, pl. 12,

fig. 1, 2.

Tests of Pseudofusulina cf. P. chiapasensis are large, inflated fusiform, and have an irregular axis of coiling. The inner three to four volutions have sharply pointed poles and convex lateral slopes, while the outer two to three volutions have bluntly rounded poles and concave lateral slopes. Specimens have from five to six volutions but the sixth volution is partly or entirely missing in all of the specimens examined. The length and width of one specimen with part of the sixth volution preserved are 14.5 mm and 8.5 mm respectively. With the exception of a decrease in the third volution of 5 out of the 7 specimens examined, the form ratio increases gradually with growth from an average of 1.2 in the first volution to maximums of 1.8 and 1.7 in the fifth and sixth volutions.

The proloculus is large, thick -walled, and spherical. The outside diameter ranges from 370 microns to 608 microns and averages 515 microns for 15 specimens. The shell shows rapid and rather uniform expansion.

The spirotheca consists of a tectum and coarse keriotheca. The 3; thickness increases rapidly to the fourth volution, then decreases slightly in the fifth and sixth volutions of most specimens. The maximum thickness in the fourth volution of 1 specimen is 250 microns.

The walls decrease in thickness toward the poles. septa are numerous and highly and narrowly fluted, and cuniculi, as well as distinct phrenotheeae, are present.

The tunnel is obscure owing to the high degree of septal fluting.

Minute chomata occur on the proloculus but do not appear to be developed beyond this. Measurements of specimens referred to this species are given in Table 5.

Remarks. This form closely resembles specimens of Pseudofusulina chiapasensis (Thompson and Miller) originally described from the

Grupera Formation in southern Mexico (33, p. 484), but it differs in that it has a greater maximum diameter, more rapid expansion and inflation, lower number of septa and a slightly smaller proloculus.

It also has smaller form ratios but shows a similar decrease in form ratio in the third volution. It is similar to specimens of ..^_Para - fusulina? turgida Thompson and Wheeler from the upper McCloud Formation

(34, p. 30-31) but differs in being more highly inflated and in having fewer septa per corresponding volution and smaller form ratios.

Occurrence. Pseudofusulina cf. P. chiapasensis is present in units 7 and 12. 34

PSEUDOFUSULINA cf. P. HAWKINSI

(Dunbar & Skinner, 1937)

Plate 6, figures 1 -3

Schwagerina hawkinsi DUNBAR & SKINNER, 1937, Univ. Texas Bull. 3701,

p. 632 -633, pl. 59; pl. 56, fig. 15, 16.

Pseudofusulina hawkinsi (DUNBAR & SKINNER). Thompson, 1948, Univ.

Kans. Paleont. Contr., Protozoa, Art. 1, p. 52.

Tests of Pseudofusulina cf. P. hawkinsi are large, inflated fusiform, and have slightly convex lateral slopes and bluntly pointed poles. The average length and diameter for 3 specimens of 6 and 7 volutions are 6.6 . mm and 4.6 mm respectively. One specimen of 7 volutions has a maximum length of 7.9 mm and a maximum diameter of

5.3 mm. The form ratio remains about the same throughout growth, and the average is about 1.5 for 6 specimens.

The proloculus is large, thick-walled, and spherical. The outside diameter in 11 specimens ranges from 365 to 475 microns and averages

418 microns. The shell expands rapidly and uniformly and shows little or no change in axial profile.

The spirotheca consists of a tectum and coarse keriotheca and increases in thickness with growth. In four specimens examined, the maximum wall thickness occurs in the sixth volution. The septa are regularly and strongly fluted. Phrenothecae and cuniculi are present.

The tunnel is obscure owing to the high degree of septal fluting.

The minute chomata seem to occur only on the proloculus. Measurements of specimens referred to this species are given in Table 6. 35

Remarks. This form closely resembles specimens of Pseudofusulina hawkinsi (Dunbar and Skinner), which was originally described from the base of the Leonard Formation in West Texas (11, p. 633), but the

Nevada form has a larger number of septa Per corresponding volution and is shorter and slightly less inflated. It differs from Pseudofusulina hessensis (Dunbar and Skinner) and P. heucoensis (Dunbar and Skinner)

in being less inflated and in having a larger form ratio and a greater number of septa. Pseudofusulina hawkinsi also occurs in the middle

Hueco Formation in West Texas (11, p. 633) and in the lower member of the Pequop Formation in east central Nevada (29, p. 106).

Occurrence. Pseudofusulina cf. P. hawkinsi is present in units 6 and 10.

PSFUDOFt;SULINA SP. A

Plate 6, figures 14-6

Tests of Pseudofusulina sp. A are of medium size, inflated fusiform, somewhat elongated, and have bluntly pointed to rounded poles.

One specimen of 6 volutions is 8.6 mm in length and 3.7 mm in width.

Form ratios of the two specimens measured are 2.0 in the first volution and 2.1 and 2.3 in the fifth and sixth volutions.

The proloculus is medium to large, subspherical to oval, and the outside diameter in three specimens ranges from 245 microns to 375 microns. The average diameter is 305 microns. The whorls are not tightly coiled and expansion is uniform.

The spirotheca consists of a tectum and fine keriotheca and is 36 of moderate thickness. The thickness gradually increases from a minimum of 20 microns in the first volution of one specimen to a maximum of 120 microns in the sixth volution of the other. Septa are numerous, irregularly spaced, and highly fluted throughout, forming high narrow septal loops and very narrow cuniculi.

The tunnel is obscure owing to the high degree of septal fluting.

Minute chomata are present only on the proloculus. Axial filling occurs in the early volutions. Measurements of specimens referred to this species are given in Table 7.

Remarks. This form greatly resembles specimens of Pseudofusulina meloformata Roberts, and may be conspecific with that species, but exact affinities cannot be determined because of the lack of properly oriented and adequately preserved specimens.

Occurrence. Pseudofusulina sp. A is present in unit 6.

PARAFUSULINA cf. P. NOSONENSIS

Thompson & Wheeler, 1946

Plate 7, figures 3 -9

Parafusulina nosonensis THOMPSON & WHEELER, 1946, Geol. Soc. Amer.

Mem. 17, pt. 1, p. 33 -34, pl. 7, fig. 1-12.

Tests of Parafusulina cf. p. nosonensis are large, elongate, and

'cylindrical in shape, and have low convex lateral slopes and bluntly rounded poles. Four specimens of 7 volutions are from 11.8 to 13.2 mm in length and 3.3 to 3.7 mm in width. The average length is 12.5 mm and the average diameter is 3.1 mm. The form ratio increases during 37 growth from an average of 1.9 for the first volution of 8 specimens to an average of 3.7 for the seventh volution of 3 specimens.

The proloculus is large and commonly irregular in shape. The average outside diameter in 23 specimens is 430 microns and the range is from 278 to 574 microns. The shell expands rather uniformly, but there is a slight elongation of the axial profile in the outer volutions.

The spirotheca consists of a tectum and relatively thin, fine keriotheca. Thickness of the spirotheca increases gradually from about

40 microns in the first volution of 7 specimens to a maximum of 120 microns in the sixth volution of 1 specimen. Septa are numerous and narrowly and highly fluted throughout the length of the shell.

Cuniculi are well developed.

The tunnel is singular, low and broad, and commonly somewhat irregular. Minute chomata are present only on the proloculus. Axial filling occurs in the inner volutions of all specimens and is commonly very dense. Specimens which have heavy axial filling also have thickened septa. Measurements of specimens referred to this species are given in Table 8.

Remarks. This form closely resembles specimens of Parafusulina nosonensis Thompson and Wheeler, which was originally described from the lower Nosoni Formation in northern California (34,(3I P. 33 -34), but it differs in being shorter and slightly more inflated, and in having chomata and heavy axial filling. It can be distinguished easily from specimens of Parafusulina californica Thompson and Wheeler by its smaller size. 38

Occurrence. Parafusulina cf. P. nosonensis is present in units

7, 10, 12 and 20.

PARAPISIILINA SP. A

Plate 6, figures 7 -10

Like Pseudofusulinella sp. A, with which it is associated, all of the specimens of Parafusulina sp. A appear to have been distorted by compression and, therefore, only measurements of the wall thickness and proloculus diameter are given here.

Tests of Parafusulina sp. A are of moderate size, elongate fusiform in shape, and have bluntly rounded poles. Three specimens have five volutions and another specimen has six.

The proloculus is spherical and of moderate size. The outside diameter in 10 specimens ranges from 183 to 276 microns and has an average of 225 microns. The shell expands rather uniformly and exhibits considerable elongation in the outer volutions; however, much of this elongation appears to be the result of compression.

The spirotheca consists of a tectum and thin keriotheca. The wall thickness increases gradually from an average of about 25 microns in the first volution to 85 and 90 microns in the fifth volution of 2 specimens. Septa are numerous and fluted throughout the shell, except for the area directly over the tunnel. Well developed cuniculi are present.

The tunnel is relatively narrow in the first three volutions, but it becomes quite broad in the fourth volution. Minute chomata are 39 present on the proloculus. Measurements of specimens referred to this species are given in Table 9.

Remarks. This form is smaller and has less fluting and a smaller proloculus than Parafusulina cf. P. nosonensis, which occurs higher in the section. It resembles other described species of Parafusulina but cannot be referred to any particular species because of the poor condition of the specimens.

Occurrence. Parafusulina sp. A is present in unit 1.

PARAFUSULINA SP. B

Plate 7, figures 1 -2

Tests of Parafusulina sp. B are of moderate size, elongate, sub - cylindrical to cylindrical, and have low lateral slopes and very bluntly rounded poles. Mature specimens appear to have five or possibly six volutions, but the outer volutions were nearly always missing in the specimens examined. One specimen of five volutions is 3.1 mm in width and 5.9 in length, and it has a form ratio of 2.9. The form ratio increases gradually with growth.

The proloculus is large and usually crushed or irregular in shape.

Its outside diameter in 6 specimens ranges from 260 to 590 microns and the average is 400 microns. The shell expands gradually with uniform elongation of the axial profile.

The spirotheca is of moderate thickness and consists of a tectum and keriotheca. The wall thickness in 7 specimens increases rapidly from an average of 40 microns in the first volution to a maximum of

I 140

100 microns in the third volution. Septa are fairly numerous and fluted throughout the length of the shell. Cuniculi are present, and heavy axial filling occurs in the axial region of the inner volutions.

The tunnel is almost entirely obscured by the septal fluting, although the dense axial filling on both sides of the tunnel area

gives the appearance of a low, broad tunnel in axial section. Minute . chomata occur on the proloculus of one of the five specimens examined.

Measurements of specimens referred to this species are given in Table

10.

Remarks. This form differs from the genotype of the genus rara- fusulina in its short cylindrical outline. It resembles specimens which occur in the Coyote Butte Formation, but it has a larger proloculus and its axial filling is confined to a greaterF degree to the axial region of the inner volutions than is true of the Coyote

Butte form.

Occurrence. Parafusulina sp. B is present in units 8, 10 and 15. 41

BIBLIOGRAPHY

1. Axelrod, Daniel I. Altitude of the Sierra Nevada and western Nevada during Mio-Pliocene time. Abstract. Geological Society of America Bulletin 66 :1527. 1955.

2. Bissell, Harold J. Silica in sediments of the upper Paleozoic of the Cordilleran area. In: Silica in sediments, ed. by H. A. Ireland. Tulsa, Oklahoma, 1959. p. 150-185. (Society of Economic Paleontologists and Mineralogists, Special Publication 7)

3. Pranson, Carl C. Bibliographic index of Permian invertebrates. Washington, D. C., 1948. 1049 p. (Geological Society of America Memoir 26)

4. Buehler, E. J. The use of peels in carbonate petrology. Journal of Sedimentary Petrology 18:71-73. 1948.

5. Chen, S. Fusulinidae of South China. Peking, 1934. 185 p. (China Geological Survey, Paleontologia Sinica, ser. P., Vol. 4, fascicle 2)

6. Cooper, G. Arthur. Permian brachiopods from central Oregon. Smithsonian Miscellaneous Collections 134 (12) :1 -79. 1957.

7. Cooper, G. Arthur et. al. Permian fauna at El Antimonio, Western Sonora, Mexico. Smithsonian Miscellaneous Collections

119(2) :1 -111. 1953. ...

8. Douglas, William B., Jr. Geology of the southern Butte Mountains, White Pine County, Nevada. In: Guidebook to the geology of east central Nevada. Intermountain Association of Petroleum Geologists, Eleventh Annual Field Conference, 1960. Salt Lake City, Utah. p. 181 -185.

9. Dunbar, Carl O. Correlation of the Permian formations of North America. Geological Society of America Bulletin 71:1763 -1806. 1960.

10. Historical geology. New York, John Wiley & Sons, Inc., 1949. 573 P.

11. Dunbar, Carl O. and John W. Skinner. Permian Fusulinidae of Texas. In: Geology of Texas, vol. 3, ed. by E. H. Sellard. Austin, 1937. p. 517 -825. (University of Texas Bulletin No. 3701)

12. Easton, H. Permian corals from Nevada and California. Journal of Paleontology 34 :S70 -583. 1960. 42

13. Ferguson, H. G. Paleozoic of western Nevada. Journal of the Washington Academy of Sciences 42 :72 -75. 1952.

14. Gianella, Vincent P. and E. R. Larson. Marine Permian at Black Rock, Nevada. Aistract. Geological Society of America Bulletin 71:2061. 1960.

15. Hill, Dorothy. The lower Carboniferous corals of Australia. Proceedings of the Royal Society of Queensland 45 :63 -115. 1934.

16. King, Philip B. The evolution of North America. Princeton, Princeton University Press, 1959. 189 p.

17. Langenheim, F. L., Jr. et al. Preliminary report on the geology of the Ely No. 3 Quadrangle, White Pine County, Nevada. In: Guidebook to the geology of east central Nevada. Intermountain Association of Petroleum geologists, Eleventh Annual Field Conference, 1960. Salt Lake City, Utah. p. 148 -156.

18. Lovejoy, Earl M. P. Mio- Pliocene Lake Nevada. In: Abstracts for 1961. New York, 1962. p. 39 -40. (Geological Society of America, Special Paper 68)

19. McLaren, D. J. and P. K. Sutherland. Lithostrotion from northeast British Columbia and its bearing on the genomorph concept. Journal of Paleontology 23 :625 -634. 1949.

20. Merriam, Charles Vi. Carboniferous and Permian corals from central Oregon. Journal of Paleontology 16:372 -381. 1942.

21. Merriam, Charles W. and S. A. Berthiaume. Late Paleozoic formations of central Oregon. Geological Society of America Bulletin 54:145 -172. 1943.

22. Merriam, Charles W. and Wayne E. Hall. Pennsylvanian and Permian rocks of the southern Inyo Mountains, California. 1957. 15.p. (U. S. Geological Survey Bulletin 1061 -A)

23. Nolan, T. B., Charles W. Merriam and J. S. Williams. The stratigraphic section in the vicinity of Eureka, Nevada. 1956. 77 p. (U. S. Geological Survey. Professional Paper 276)

24. Osmond, John C. Tectonic history of the Basin and Range Province

in Utah and Nevada. Abstract. Mining Engineering 10:1132 -1134. . 1958.

25. Roberts, Ralph J. Geology of the Antler Peak Quadrangle, Nevada. 1951. 1 sheet. (U. S. Geological Survey. Geologic Quadrangle Map no. 10) S.

26. Paleozoic structure in the Great Basin. Abstract. Geological Society of America Bulletin 71 :1955. 1960.

27. Sharp, Byron J. Uranium deposits in volcanic rocks of the Basin and Range Province. 1955. p. 79-83. (U. S. Geological Survey, Professional Paper 300)

28. Smith, S. and W. D. Lang, Descriptions of the type -specimens of some Carboniferous corals of the genera "Diphyphyllum ", "Stylastraea ", Aulophyllum, and Chaetetes. Annals and Magazine of Natural History, ser. 10, 50 :177 -194. 1930.

29. Steele, Grant. Pennsylvanian-Permian stratigraphy of east- central Nevada and adjacent Utah. In: Guidebook to the geology of east central Nevada. Intermountain Association of Petroleum Geologists, Eleventh Annual Field Conference, 1960. Salt Lake City, Utah. p. 91 -113.

30. Stehli, Francis Greenough. Lower Leonardian Brachiopoda of the Sierra Diablo. American Museum of Natural History Bulletin 105 :263 -358. 1954.

31. Thompson, M. L. American Wolfcampian fusulinids. Topeka, 1954. - 225 p. (University of Kansas Paleontological Contributions: Protozoa, art. 5)

32. American Studies of fusulinids. Topeka, 1948. - 184 p. (University of Kansas Paleontological Contributions: Protozoa, art. 1)

33. Thompson, M. L. and A. K. Miller. The Permian of southernmost Mexico and its fusulinid faunas. Journal of Paleontology 18:481 -504. 1944.

34. Thompson, M. L., Harry Wheeler and J. C. Hazzard. Permian fusulinids of California. Washington, D. C., 1946. 77 p. (Geological Society of America Memoir 17)

35. Visher, F. N. Geology and ground -water resources of Quinn River Valley, Humboldt County, Nevada. Carson City, 1957. 55 p. (Nevada, Office of State Engineer, Water Resources Bulletin no. 14) 4/ 4

APPENDIX 45

LITHOLOGIC DESCRIPTIONS AND FAUNA

(Measured from the base upward)

Uhit Thickness Lithology and Fauna Number in Feet

1 4 Limestone, thin -bedded, light brownish gray, weathering brown to tan; contains carbonate fossils in a fine -grained chart matrix. Climacammina sp., Pseudofusulinella sp. A., Parafusulina sp. A, Rhombotrypella sp., unidentified brachiopods, crinoid columnals.

2 (9) Rhyolite sill, light tan, weathering tan to reddish brown, highly weathered. Tertiary?

3 8 Limestone, medium bedded, brownish gray, weathering brown to buff, numerous calcite veins, colonial coral in a carbonate matrix. Lithostrotion sp., genomorphs Diphyphyllum and Diphystrotion.

4 (3) Rhyolite sill, light tan, weathering tan to reddish brown, highly weathered. Tertiary?

5 89 Limestone, massive, light brown, weathering light brown to buff, fine -crystalline; contains cherty seams and irregular masses which become more abundant toward the top. No fossils observed.

6 228 Limestone, dark gray to black, weathering dark gray, organic debris in a matrix which grades from coarse -crystalline at the bottom to micro - crystalline at the top; contains pink and white calcite veins and numerous gray chert seams and irregular stringers which give a thin-bedded appearance to the unit. Climacammina sp., Geinitzina sp., Schubertella aff. S. kingi, Pseudofusulinella cf. P. occidentalis, Triticites? sp., Pseudofusulina cf. P. hawkinsi, Pseudofusulina sp. A.unidentified bryozoan andbrachiopods, worm tubes ?, crinoid columnals.

Fault

7 548 Limestone, black, weathering dark gray, organic debris in a microcrystalline matrix; contains calcite veins and chert seams and irregular 116

Unit Thickness Lithology and Fauna Number in Feet

stringers which give a thin -bedded appearance to the bottom of the unit but which decrease in abundance toward the top; a few oolites occur in the top beds and a one -foot bed of colonial corals is present near the middle of the unit. Clima- cammina sp., Geinitzina sp., Schubertella sp., Pseudofusulinella aff. P. utahensis, Triticites? sp., Pseudofusulina cf. P. chiapasensis, Para - fusulina cf. P. nosonensis, Waagonophyllum sp., unidentified gastropod, crinoid columnals.

8 90 Limestone, thick bedded, medium gray, weathering light gray to tan, fine -crystalline calcareous and cherty matrix; contains a few chert seams and irregular masses, some fossils partly silicified. Climacammina sp., Staffella sp., Parafusu- line sp. B, unidentified horn coral, bryozoans and-brachiopods, crinoid columnals. r. 9 57 Limestone, thick bedded, tan, weathering very light tan to buff, fine -crystalline; contains a few calcite veins. No fossils observed.

10 450 Limestone, thick bedded, dark gray, weathering medium gray to reddish gray in the top beds, organic debris in a microcrystalline matrix; contains white, pink and tan calcite veins and a few chert seams and irregular masses. Climacammina sp., Cribrostomum sp., Geinitzina sp., Schubertella sp., Pseudofusulinella aff. P. utahensis, Pseudofusulina cf. P. hawkinsi, Parafusulina cf. P. noeonensis, Párafusulina sp. E, crinoid columnáls.

11 9 Chert conglomerate, thick -bedded, fine to medium - sized subangular black, gray and red chert and metaquartzite pebbles in a tan and red fine - grained porous chert matrix. No fossils observed.

12 21 Limestone, medium to thick- bedded, dark brownish gray, weathering gray and tan, organic debris in a microcrystalline calcite and chert matrix; contains numerous small calcite veins. Clima- cammina sp., Geinitzina sp., Textularia sp., Staffella sp., Schubertella sp., Pseudofusulinella cf. P. occidentalis, Pseudofusulina cf. P. chiapasensis, Parafusulina cf.P. nosonensis, 147

Unit Thickness Lithology and Fauna Number in Feet

Rhombotrypella sp., unidentified brachiopods and gastropods, crinoid columnals.

13 76 Limestone, medium-bedded, light gray, weathering light gray to tan, fine -crystalline; contains pink and tan calcite veins and a few chert seams and irregular masses. No fossils observed.

14 50 . Limestone, medium- bedded, dark gray, weathering medium gray, microcrystalline; contains white and tan calcite veins and some chert seams and irregular masses. Schubertella sp., worm tubes?

15 413 Limestone, medium- bedded, dark gray to brownish gray, weathering medium gray to brownish and reddish gray in places, organic debris in a fine to microcrystalline matrix; contains white, orange and tan calcite veins and some cherty beds and chert seams and irregular masses. A one -foot colonial coral bed is present near the middle of the unit. Schubertella sp., Pseudo - fusulinella cf. P. occidentalis, Parafusulina sp. B, Waagonop111um sp., crinoid columnals.

16 37 Chert, medium- bedded, dark brown and gray, weathering brown and reddish brown to black, fine -grained; contains minute iron oxide and carbonate inclusions. No fossils observed.

1 Fault ,1

17 75 Limestone, thick-bedded, medium gray, weathering medium to light gray, microcrystalline; contains some calcite veins and irregular chert masses. Schubertella sp.?

18 87 Limestone, thick bedded, dark gray to black, weathering dark to medium gray, fine -crystalline; contains numerous calcite veins and chert seams and irregular masses which increase in abundance toward the top of the unit. The top beds contain numerous poorly preserved and unidentified coral fragments.

19 21 Limestone, thin to medium-bedded, black, weathering black, microcrystalline; contains short, thin chert seams and a few irregular chert masses. l8

Unit Thickness Lithology and Fauna Number in Feet

The top one foot of the unit is thin-bedded and very black and cherty. Contains a few poorly preserved and unidentified fusulinid fragments.

20 352 Limestone, thin to medium -bedded, thick beds at the top, dark to medium gray and brownish gray, weathering brown and tan, organic debris in a microcrystalline calcite and fine -grained chert matrix, beds become very siliceous toward the top of the unit; contains numerous chert beds, seams and irregular masses and some calcite veins. Climacammina st., Cribrostomum sp., (?einit ?ina sp., Textularia sp., Staffella sp., Schubertella sp., Para usulina cf. nosonensis, unidentified horn corals, Rhombotrypella sp., worm tubes ?, Stenoscisma sp., Schuchertella

sp., . Derbyia sp., Chonetes sp., Rhipidomella sp., Spiriferella sp.,Spiriferina cf. S. billingsi, Punctospirifer aff. P. campestris, Dialasma sp., product id fragments and unidentified brachiopods, Baylea sp., unidentified gastropods, crinoid columnals,

2615 49

Table 1. Measurements of Thseudofusulinella, cf. P. occidentalis

Half length in mm. Radius vector in mm.

Specimen 1 2 3 Specimen 1 2 3 Volution Volution 1 0.1 0.1 0.1 1 0.1 0.1 0.1

2 0.2 0.1 0.2 2 ` 0.1 0.1 0.1 3 0.3 0.2 0.2 3 0.1 0.2 0.1

4 0.4 0.4 0.4 11 0.2 0.3 0.2 5 0,7 0.6 0.6 5 0.11 0.4 0.3 6 0.9 0.7 0.3 6 0.5 0.5 0.4 7 1.2 0.9 1.1 7 0.7 0.6 0.6 8 1.4 1.1 1.4 8 0.9 0.8 0.9 9 1.9 1.5 2.0 9 1.2 1.0 1.2

Form ratio Wall thickness in microns

Specimen 1 2 3 Specimen 1 2 3 4 Volution Volution

1 1.9 1.1 : 1.4 ' 1 -- - 12 -- 2 2.1 1.2 2.3 2 26 19 21 30 3 2.0 1.4 2.0 3 32 30 27 47 4 1.9 1.5 2.3 4 45 32 40 58 5 1.9 1.6 2.2 5 60 40 77 60 6 1.8 1.6 2.2 6 70 49 80 65 7 1.6 1.4 1.7 7 55 93 -- 80 8 1.6 1.4 1.6 8 65 75 -- 93 9 1.6 1.6 1.7 9 83 - -- 107

Septal Count Outside diameter of proloculus in microns

Specimen 5 Specimen 3 11 6 Volution Diameter 94 118 132 1 -- 2 20 3 21 4 26 5 31 6 -- 7 -- 8 -- 9 -- 50

Table 2. Measurements of "seudofusulinella aff. P. utahenaais

Half length in m.

Specimen 1 2 3 4 5 6 Volution 1 0.1 0.2 0.1 0.2 0.2 0.2 2 0.2 0.3 0.3 0.3 0.3 0.3 3 0.4 0.5 0.4 0.6 0.5 0.5 4 0.7 0.7 0.7 0.9 0.7 0.7 5 1.1 1.0 1.0 1.4 1.1 1.0 6 1.5 1.4 1.4 ._.. ..._. .. 7 2.0 1.9 2.0 OMAN.. -- ---

Radius vector in mm.

Specimen 1 2 3 11 5 6

Volution - 1 0.1 0.1 0.1 0.1 0.1 0.1 2 0.2 0.2 0.2 0.2 0.2 0.2 3 0.3 0.3 0.3 0.3 0.3 0.11 4 0.5 0.5 0.5 0.5 0.11 0.6 5 0.7 0.8 0.8 0.7 0.7 0.8 6 1.0 1.1 1.0 0.9 .-.- --- 7 1.4 1.4 --- ...._ ...

Form ratio

Specimen 1 2 3 4 6 -- - 5

Volution - 1 1.0 1.5 1.3 1.5 1.6 1.2 2 1.1 1.4 1.4 1.7 1.5 1.3 3 1.2 1.4 1.2 1.8 1.7 1.4 4 1.4 1.4 1.4 2.0 1.7 1.3 5 1.5 1.3 1.3 1.9 1.6 1.4 6 1.5 1.3 1.4 ------.. 7 1.5 1.4 --- M M ..... 51

TablE: 2 (continued)

Wall thickness in microns

Specimen 1 2 3 4 5 6 . 7 Volution ` 1 32 25 25 30 21 25 22 2 39 37 35 45 27 52 40 3 46 42 -- 46 45 45 -- 4 50 -- 70 -- 61 60 -- 60 5 40 55 67 -- -- - 6 60 85 7 70 -- -_ Mime 4» - --

Septal count

Specimen 8 Volution 1 12 2 16 3 20 4 -- 5 -- 6 -- 7 --

Outside diameter of proloculus in microns

Specimen 1 2 3 4 5 6 7 8 Diameter 140 138 120 110 130 132 122 134 52

Table 3. Measurements of Pseudofusulinella sp. A

Wall thickness in microns

Specimen 1 2 3 4 5 6 Volution 1 33 11 45 17 35 34 2 38 27 45 40 53 50 3 55 35 60 64 65 55 4 89 50 95 60 80 95 5 88 55 105 88 -- -- 6 100 ------

Septal count

Specimen 7 8 9 Volution 1 9 10 -- 2 13 12 13 3 18 15 15 4 21 17 -- 5 -- - -- 6 ------

Outside diameter of proloculus in microns

Specimen 1 2 3 4 5 6 7 Diameter 140 117 150 114 160 164 112

Specimen 10 11 12 13 14 15 16 Diameter 136 200 175 145 150 137 218 53

Table 4. Measurements of Triticites? sp.

Half length in mm.

Specimen 1 2 3 4 5 6 7 Volution

1 - _ 2 0.2 0.2 0.2 0.2 0.2 0.2 0.1 3 0.3 0.3 0.3 0.3 0.3 0.4 0.3 4 0.4 0.5 0.5 0.5 0.4 0.5 0.5 5 0.7 0.7 0.7 0.7 0.7 0.8 --- 6 1.1 0.9 1.2 1.1 1.0 ------7 1.5 1.4 ------

Radius vector in mm.

Specimen 1 2 3 4 5 6 7 Volution 1 ------__ --- ..__ --- --_ 2 0.2 0.1 0.1 0.1 0.1 0.1 0.1 3 0.2 0.2 0.2 0.2 0.2 0.2 0.2 4 0.3 0.3 0.3 0.3 0.3 0.4 0.3 5 0.4 0.4 0.4 0.4 0.5 0.5 --- 6 0.6 0.5 0.5 0.5 ...._ ._.. ° - - 7 0.9 0.8 ------=

Form ratio

Specimen 1 2 3 ' 4 5 6 7 Volution 1 --- _ 2 1.0 1.6 1.2 1.7 1.3 1.3 1.3 3 1.1 1.6 1.4 1.9 1.3 1.6 1.6 4 1.3 1.7 1.9 1.9 1.5 1.4 1.7 5 1.6 1.8 1.9 2.1 1.6 1.4 --- 6 1.8 1.8 2.2 ------7 1.8 1.8 ------54

Table 4 (continued)

'a11 thickness in microns

Specimen 1 2 3 4 5 6 7 Volution 1 17 13 11 -- 10 12 12 2 28 15 16 17 14 21 -- 3 32 21 20 26 23 30 30 4 35 26 39 35 34 51 5 47 47 43 54 55 45 -- 6 74 60 73 -- --. -- -- 7 55 68 ------

Septal Count

Specimen 8 9 10 11 12 Volution 1

2 . 8 8 8 8 7 3 10 10 11 10 10

14 11 11 13 13 13 5 13 13 17 15 -- 6 16 17 -- 17 -- 7 ------

Outside diameter of proloculus in microns

Specimen . 1 2 3 5 6 7 _ 9 11 12 13 14

Diameter 120 90 100 84 56 76 - 63 - 0 83 90 85 55

Table 5. Measurements of Pseudofusulina cf. P. chiapasensis

Half length in mm.

Specimen 1 2 3 4 5 6 7 Volution 1 --- 0.6 0.3 0.4 1.0 0.7 1.3 2 2.3 1.7 0.9 1.3 2.2 1.5 2.5 3 3.3 2.4 1.9 2.2 3.4 2.2 3.8 4 4.3 3.3 3.1 2.9 5.1 3.2 4.4 5 6.2 4.3 4.0 4.2 6.6 _-_. ...._ 6 7.2 _._ _.. .r......

Radius vector in mm.

Specimen 1 2 3 4 5 6 7 Volution 1 --- 0.5 0.3 0.3 1.0 0.5 1.1 2 1.6 0.9 0.8 0.8 1.9 1.0 1.9 3 2.5 1.5 1.7 1.4 2.6 1.6 2.4 4 3.1 2.1 2.4 2.2 3.2 2.2 3.1 5 3.8 2.7 2.9 2.8 3.8 ------6 4.3 ___ r._ r.,. _.._ .- _.._

Form ratio

Specimen 1 2 3 4 5 6 7 Volution 1 1.2 1.3 1.2 1.4 1.0 1.4 1.2 2 1.4 1.9 1.3 1.6 1.1 1.6 1.3 3 1.4 1.6 1.1 1.5 1.3 1.3 1.6

4 1.4 1.6 1.3 1.3 1.6 ' 1.5 1.5 5 1.6 1.6 1.4 1.5 1.8 ------6 1.7 a ...... ------_ 56 Table 5 (continued)

Wall thickness in microns

Specimen 1 2 3 4 5 6 7 Volution 1 85 78 36 25 62 64 95 2 loo 100 47 38 77 78 150 3 130 113 55 45 110 114 190 4 252 238 70 82 110 160 --- 5 180 155 81 88 120 ------6 ------._ .

Septal count

Specimen 8 9 10 11 12 13 14 15 Volution 1 8 10 11 11 11 11 9 11 2 16 15 15 15 15 17 15 16 3 19 22 21 26 22 21 20 20 4 26 29 32 32 31 ------5 37 31 38 ------6 39 142 --

Outside diameter of proloculus in microns

Specimen 2 3 !t 5 6 8 10 11 Diameter 556 375 371 452 608 522 490 605

Specimen 12 13 14 16 17 18 19 Diameter 490 580 375 565 600 546 390 57

Table 6. Measurements of Pseudofusulina cf. P. hawkinsi

Half length in mm.

Specimen 1 2 3 4 5 6 Volution 1 0.7 0.6 0.4 0.7 0.5 0.6 2 1.0 0.9 0.6 1.3 1.1 1.1 3 1.4 1.2 1.0 1.9 1.8 1.6 4 1.9 1.7 1.4 2.3 2.6 2.7 5 2.5 2.3 1.8 3.3 --- _.,.- 6 3.0 3.1 3.0 --- - -...- 7 --- 3.9 - - -...- " -

Radius vector in mm.

Specimen 1 2 3 4 _ 5 6 Volution 1 0.5 0.4 0.3 0.4 0.4 0.4 2 0.9 0.6 0.4 0.7 0.7 0.7 3 1.2 0.9 0.7 1.1 1.1 0.9 4 1.6 1.3 1.1 1.6 1.5 1.5 5 2.0 1.7 1.5 1.9 --- 2.0 6 2.3 2.2 1.9 ------7 --- 2.7 ------

Form ratio

Specimen 1 _ 2 3 4 5 6 Volution 1 1.3 1.6 1.6 1.9 1.5 1.5 2 1.2 1.4 1.5 1.9 1.6 1.6 3 1.2 1.3 1.4 1.7 1.7 1.7 4 1.2 1.3 1.4 1.5 1.8 1.8 5 1.3 1.4 1.2 1.7 ------6 1.3 1.4 1.6 --- --.-- --- 7 --- 1.5 ------M 58

Tale 6 (continued)

Wall thickness in microns

Specimen 1 2 3 4 5 6

Volution ,

1 .-, --- w 74 . 35 2 88 62 --- 61 80 tai 3 100 90 65 72 134 88 4 117 100 85 81 145 115 5 190 97 100 96 125 137 6 192 115 141 130 ------7 118 109 --- 100 --- NO

Septal count

Specimen 1 2 3 ta , 5 6 Volution 1 10 10 10 10 10 10 2 15 15 17 18 18 17 3 16 22 15 23 23 20 4 23 26 23 29 -- -- 5 24 27 -- -_ -- ..._ 6 .... -- -- .... -- -- 7

Outside diameter of proloculus in microns

Specimen 1 2 3 4 5 6 Diameter 475 470 285 442 380 345

Specimen 7 8 9 10 11 12 Diameter 310 385 372 265 410 438 59

Table 7. Measurements of Pseudoftsulina sp. A

Wall thickness in microns Half length in mm. Radius vector in mm.

Specimen 1 2 Specimen 1 2 Specimen 1 2 Volution Volution Volution 1 -- 20 1 0.3 0.3 1 0.2 0.2 2 40 40 2 0.6 0.7 2 0.3 0.3 3 54 48 3 1.1 1.2 3 O. 0.5 4 63 .._. 4 1.9 1.9 4 0.9 0.8 5 70 80 5 2.7 2.4 5 1.4 1.2 6 120 -- 6 4.3 --- 6 1.9 ---

Form ratio Septal count

Specimen 1 2 Specimen 3 4 Volution Volution 1 2.0 2.0 1 10 10 2 2.5 2.7 2 15 15 3 2.2 2.6 3 22 22

14 2.0 2.3 4 -- -- 5 2.0 2.1 -- -- 6 2.3 --- 5 -- --

Outside diameter of nroloculus in microns

Specimen 2 3 4 Diameter 2115 375 325 60

Table 8. Measurements of Parafusulina cf. P. nosonensis

Half length in mm.

Specimen 1 2 3 4 5 6 7 8 Volution 1 .5 .8 .4 .5 .6 .6 .5 .5 2 .8 1.7 .6 1.1 1.1 1.0 1.1 1.1 3 1.1 2.5 1.3 1.4 2.1 1.9 1.7 1.8 4 2.0 3.9 2.1 2.1 3.5 2.5 2.6 2.6 5 3.0 4.9 3.5 3.1 4.7 3.0 3.3 3.5 6 4.5 5.7 5.0 4.5 5.6 ------7 5.9 6.2 6.6 5.5 - - - -..-

Radius vector in mm.

Specimen 1 2 3 4 5 6 7 8 Volution 1 .3 .3 .2 .3 .4 .3 .3 .3 2 .4 .5 .4 .5 .5 .4 .4 .4 3 .6 .7 .5 .6 .7 .6 .7 .6 4 .8 .9 .8 .8 1.0 .8 .9 .8 5 1.1 1.1 1.1 1.1 1.2 1.0 1.2 1.1 6 1.3 1.3 1.4 1.4 1.6 ------7 1.6 1.7 1.8 ------M-

Form ratio

Specimen 1 2 3 4 5 6 7 8 Volution 1 2.0 2.4 1.6 2.0 1.7 2.0 1.8 1.9 2 2.1 3.2 1.7 2.2 2.1 2.3 2.4 2.6 3 1.9 3.8 2.5 2.2 2.9 3.1 2.6 3.0 4 2.6 4.6 2.7 2.6 3.5 3.1 2.9 3.1 5 2.8 4.5 3.3 3.0 3.8 2.9 2.7 3.1 6 3.5 4.4 3.4 3.3 3.6 ------7 3.7 3.8 3.7 ------61

Table 8 (continued)

Wall thickness in microns

Specimen 1 2 4 5 6 7 8 Volution

1 35 45 30 . 45 30 35 40 2 40 55 30 45 40 35 34 3 50 58 41 60 48 55 55 4 42 80 52 68 57 70 64 5 63 90 60 95 61 -- -- 6 78 80 78 120 ------7 80 _ M -- -- -

Septal count

Specimen 9 10 11 12 13 14 15 16 Volution

1 11 . 11 10 11 11 11 10 11 2 22 17 16 16 16 15 16 17

3 24 , 20 18 20 22 18 24 19 4 25 26 25 26 22 20 24 21 5 24 31 22 24 25 22 -- -- 6 ------_. - - 7 ------

Outside diameter of proloculus in microns

Specimen 1 2 3 4 5 6 7 8 9 Diameter 354 378 372 386 421 -445 454 420 566

Specimen 10 . 11 12 13 14 15 16 17 18 Diameter 408 392 477 289 278 453 323 448 400

Specimen 19 20 21 22 23 24 25 26 27 Diameter 574 500 408 564 389 450 468 356 440

J 62

Table 9. Measurements of Parafusulina sp. A

Wall thickness in microns

Specimen 1 2 3 4

Volution . 1 21 36 -- 23

2 > 31 40 25 36 3 55 83 41 65 4 64 84 77 80 5 85 90 ..- ....

Septal count

Specimen 5 6 7 8 9 10

Volution . 1 --- 9 9 9 9 -- 2 12 12 14 14 13 13 3 17 20 17 17 17 17 __ M.N. 4 24 . M -- 5 26 - -- ______

Outside diameter of proloculus in microns

Specimen 1 2 3 4 7 11 12 13 14 15 Diameter 188 183 233 230 255 276 220 222 238 191

L 63

Table 10. Measurements of Parafusulina sp. B

Half length in mm. Radius vector in mm.

Specimen 1 2 3 4 Specimen 1 2 3 4 Volution Volution 1 0.2 ------1.1 1 0.2 0.2 0.4 0.5 2 0.7 0.8 1.3 1.8 2 0.3 0.5 0.7 0.7 3 0.9 1.0 1.8 2.6 3 u.4 0.6 0.9 1.0 4 --- 1.9 2.6 3.5 4 --- 0.8 --- 1.2 5 --- 4.5 5 -. - __.. 1.5

Wall thickness in microns

Specimen 1 2 3 4 5 6 7 Volution 1 -- 45 -- 48 36 -- 46 2 18 58 55 70 40 64 72 3 -- 62 76 100 55 80 90 4 -- -- 85 100 60 95 97 5 ------78 - -- --

Septal count

Specimen 8 9 Volution 1 10 8 2 18 15 3 21 24 4 - -- 5 +- --

Outside diameter of proloculus in microns

Specimen 1 2 3 4 5 8 Diameter 262 342 463 590 589 260 .t

EXPLANATION OF PLATE 3

Figure

1 Schubertella aff. S. kingi DUNBAR & SKINNER, 1937. Axial section from unit b, X40.

2 -ti Pseudofusulinella aff. P. utahensis THOMPSON & BISSELL, 1954. Axial sections from unit 7; 2, X 40; 3-4, X 10.

5-7 Pseudofusulinella cf. P. occidentalis (THOMPSON & WHEELER, 1946). 5, Axial section from unit 6, X 10; 6, axial section from unit 12, X 10; 7, sagital section from unit 12, X 40.

8 -9 Pseudofusulinella sp. A. 8, Axial section; 9, sagital section; both from unit 1 and both X 10.

10 -16 Triticites? sp. 10 -12, Axial sections; 13 -14, tangential sections showing cuniculi; 15, sagital section; all from unit 7 and all X 20; 16, tangential section from unit 6 showing cuniculi, X 40. 65

PLATE 3

J..' '10 11. "

8 9

13 fr--1110j. J 14,

haw. ae -

- r411,4 4 t' 441" 14 4'44`-'44}411,44.-T014-4- '5 16 EXPLANATION OF PLATE 4

Figure

1 -5 Triticites? sp. 1, 4, Axial sections; 2, 5, tangential sections showing cuniculi; 3, tangential section showing lack of septal fluting across the central part of the test; all from random samples collected by D. A. Bostwick and all X 10.

6 -7 Pseudofueulïna cf. P. chiapasensis (THOMPSON & MILLER, 1944). 6, Axial section showing phrenothecae; 7, tangential section showing cuniculi; both from unit 12 and both X 10.

l 67

PLATE 4

1.Win 2 _, :?,.oelI1`P. - . rA.6 3 r 10:

row' 5 ot. 4 N., I ..ei

ON? a - *it.*

I -{401/4:

1 .,:o 4 6 ^ *, ~+ V !ìt i f' 3 ~-- 0 - ,- Sc ii : , i t at e .../e ~ ,, 7 - ..; '. S.--.Artr it , 1, "4: - '-N iL .

Wk.. ..4'1;14V7.. :.: Ifel. -t 1:.-'-'''' A . Ft' N. T.. ACI,`- -14.41:3:4 ' EXPLANATION OF PLATE 5

Figure

1-8 Pseudofusulina cf. P. chiapasensis (THOMPSON & MILLER, 1944). 1 -2, Axial sections from unit 12 showing phrenothecae; 3, sagital section from unit 12; 4 -5, axial sections from unit 7; 6, 8, sagital sections from unit 7 showing phrenothecae; 7, tangential section from unit 7 showing cuniculi; all X 10. 69

PLATE 5

6 7 rl

EXPLANATION OF PLATE 6

Figure

1 -3 Pseudofusulina cf. P. hawkinsi (DUNBAR & SKINNER, 1937). 1, Sagital section, X 10; 2, axial section, X 10; 3, tangential section showing cuniculi, X 20; all from unit 10.

4-6 Pseudofusulina sp. A. 4, Axial section, X 10; 5, sagital section, X 10; 6, tangential section showing cuniculi; all from unit 6.

7 -10 Parafusulina sn. A. 7-8, Axial sections; 9, tangential section showing cuniculi; 10, sagital section; all from unit 1 and all X 10. 71

PLATE 6

1:1 5

ti 2 ,

, ,

h-,4 411411r. ..,-'^` ; i ,, /. ' ,;, :,!+,l,= :A 0. f_ _

. 7

8 EXPLANATION OF PLATE 7

Figure

1 -2 Parafusulina. sp. B. 1, Axial section; 2, tangential section showing cuniculi; both from unit 8 and both X 10.

3 -9 Parafusulina cf. P. nosonensis THOMPSON & WHALER, 1946. 3, Tangential section from unit 7 showing cuniculi, X 10; 4, axial section from unit 20, X 9; 5, 8, sagital sections from unit 20, X 10; 6, 9, axial sections from unit 20, X 10; 7, tangential section from unit 20, X 10. 73

PLATE 7 EXPLANATION OF PLATE 8

Figure

la.; 2 -3, X 2; 1 -4 I'.hor1otrynella sp. 1 -3, Cross sections; 1, X unit 20. ?a, longitudinal section, X 2; all from

hyl1ui and Diphystrotion. 5-7 Lithostrotion sp., genomorphs Diph 5, Longitudinal section; 5a, X 2; ,9o, X 1; 6, Dipt'p llum,, cross section; 6a, X 2; 6b, X 1; 7, Diphystrotion cross section; 7a, X 2; 7t, X 1; all from unit 3. l

PLATE 8

mmovar...... ,--,.

-,4et t 4 r

L - b '6,41e 5 a

6 EXPLANATION OF PLATE 9

Figure

1-6 T,aaganophyllum sp. 1 -3, 5-6, Cross sections; 4, longi- tudinaf section; la, 4, 5a, 6a, X 2; 2a & 3a, p 3; lb, 2b, 3b, 5b, 6b, X 1. Figures 1-4 are from unit 7; figures 5-6 are from unit 15. T1

? \..., a. 9

' '7;14 et 2 o b b

'6 b

0 5 o 6 b 't)